Late Paleozoic icehouse

From Wikipedia, the free encyclopedia
(Redirected from Karoo Ice Age)
Approximate extent of the Karoo Glaciation (in blue), over the Gondwana supercontinent during the Carboniferous and Permian periods

The late Paleozoic icehouse, also known as the Late Paleozoic Ice Age (LPIA) and formerly known as the Karoo ice age, was an ice age that began in the Late Devonian and ended in the Late Permian,[1] occurring from 360 to 255 million years ago (Mya),[2][3] and large land-based ice-sheets were then present on Earth's surface.[4] It was the second major icehouse period of the Phanerozoic. It is named after the tillite (Dwyka Group) found in the Karoo Basin of western South Africa, where evidence for the ice age was first clearly identified in the 19th century.[5]

The tectonic assembly of the continents of Euramerica and Gondwana into Pangaea, in the Hercynian-Alleghany Orogeny, made a major continental land mass within the Antarctic region, and the closure of the Rheic Ocean and Iapetus Ocean saw disruption of warm-water currents in the Panthalassa Ocean and Paleotethys Sea and an increase in carbon sequestration via silicate weathering, which led to progressive cooling of summers, and the snowfields accumulating in winters, which caused mountainous alpine glaciers to grow, and then spread out of highland areas. That made continental glaciers, which spread to cover much of Gondwana.[6]

Data from Serpukhovian and Moscovian marine strata of South China point to glacioeustasy being driven primarily by long-period eccentricity, with a cyclicity of about 0.405 million years, and the modulation of the amplitude of Earth's obliquity, with a cyclicity of approximately 1.2 million years. This is most similar to the early part of the Late Cenozoic Ice Age, from the Oligocene to the Pliocene, before the formation of the Arctic ice cap, suggesting the climate of this episode of time was relatively warm for an icehouse period.[7] Evidence from the Middle Permian Lucaogou Formation of Xinjiang, China indicates that the climate of the time was particularly sensitive to the 1.2 million year long-period modulation cycle of obliquity. It also suggests that palaeolakes such as those found in the Junggar Basin likely played an important role as a carbon sink during the later stages of the LPIA, with their absorption and release of carbon dioxide acting as powerful feedback loops during Milankovitch cycle driven glacial and interglacial transitions.[8]

Interpretations of the LPIA vary, with some researchers arguing it represented one continuous glacial event and others concluding that as many as twenty-five separate ice sheets across Gondwana developed, waxed, and waned independently and diachronously over the course of the Carboniferous and Permian,[9][10][11] with the distribution of ice centres shifting as Gondwana drifted and its position relative to the South Pole changed.[12] At the beginning of the LPIA, ice centres were concentrated in western South America; they later shifted eastward across Africa and by the end of the ice age were concentrated in Australia.[13] Evidence from sedimentary basins suggests individual ice centres lasted for approximately 10 million years, with their peaks alternating with periods of low or absent permanent ice coverage.[14] The glacial episodes that occurred during the late Famennian and late middle to early late Tournaisian are sometimes considered discrete glaciations separate from and preceding the LPIA proper that began between 335 and 330 Mya during the Viséan or Serpukhovian.[11][15][16][17][18] Likewise, the more geographically limited glaciations that persisted in some parts of Gondwana until the last alpine glaciers melted in what is now eastern Australia around 255 Mya[3] are sometimes not considered part of the LPIA proper either, which is said to have peaked during the Asselian and early Sakmarian and ended in the late Sakmarian around 290 Mya[15] or near the Artinskian-Kungurian boundary[2] and the associated Kungurian Carbon Isotopic Excursion under this more restricted definition.[19][20][21]

At least two major periods of glaciation within the LPIA proper are known:

  • The first glacial period occurred from the Serpukhovian to the Moscovian: ice sheets expanded from a core in southern Africa and South America. A relatively warm interglacial interval spanning the Kasimovian and Gzhelian, coinciding with the Alykaevo Climatic Optimum, occurred between this first major glacial period and the later second major glacial period.[22]
  • The second glacial period occurred from the late Gzhelian across the Carboniferous-Permian boundary to the early Sakmarian; ice sheets expanded from a core in Australia and India.[2] From the late Sakmarian onward, and especially following the Artinskian Warming Event (AWE),[23] these ice sheets declined, as indicated by a negative δ18O excursion.[11]

Other, minor or more geographically limited glacial intervals have also been identified:

  • The aforementioned interval of transient glaciations spanning from the Famennian to the late Visean or earliest Serpukhovian.[17][11]
  • A glacial interval limited to Australia spanning the latest Sakmarian and the Artinskian, known regionally as P2 (P1 coinciding with the Gondwana-wide glaciations during the Asselian and early Sakmarian). This regional glaciation occurred amidst a global pulse of net warming and deglaciation, as evidenced by the retreat of ice sheets in Central Africa and in the Karoo Basin.[24]
  • A second, longer regional interval also limited to Australia from the middle Kungurian to the early Capitanian, known as P3. Unlike the previous glaciations, this one and the following P4 glaciation were limited to alpine glaciation.[25]
  • A final regional Australian interval lasting from the middle Capitanian to the late Wuchiapingian, known as P4.[26] This glacial period was interrupted by a rapid warming interval corresponding to a surge in activity from the Emeishan Traps and corresponding Capitanian mass extinction event.[27]

The time intervals here referred to as glacial and interglacial periods represented intervals of several million years corresponding to colder and warmer icehouse intervals, respectively, were influenced by long term variations in palaeogeography, greenhouse gas levels, and geological processes such as rates of volcanism and of silicate weathering and should not be confused with shorter term cycles of glacials and interglacials that are driven by astronomical forcing caused by Milankovitch cycles.[28]

Late Paleozoic glaciations[edit]

Timeline of glaciations (ice ages), shown in blue

According to Eyles and Young, "Renewed Late Devonian glaciation is well documented in three large intracratonic basins in Brazil (Solimoes, Amazonas and Paranaiba basins) and in Bolivia. By the Early Carboniferous (c. 350 Ma) glacial strata were beginning to accumulate in sub-Andean basins of Bolivia, Argentina and Paraguay. By the mid-Carboniferous glaciation had spread to Antarctica, Australia, southern Africa, the Indian Subcontinent, Asia and the Arabian Peninsula. During the Late Carboniferous glacial accumulation (c. 300 Ma) a very large area of Gondwana land mass was experiencing glacial conditions. The thickest glacial deposits of Permo-Carboniferous age are the Dwyka Formation (1000 m thick) in the Karoo Basin in southern Africa, the Itararé Group of the Paraná Basin, Brazil (1400 m) and the Carnarvon Basin in eastern Australia. The Permo-Carboniferous glaciations are significant because of the marked glacio-eustatic changes in sea level that resulted and which are recorded in non-glacial basins. Late Paleozoic glaciation of Gondwana could be explained by the migration of the supercontinent across the South Pole."[29]

In northern Ethiopia glacial landforms like striations, rôche moutonnées and chatter marks can be found buried beneath Late Carboniferous-Early Permian glacial deposits (Edaga Arbi Glacials).[30] Glaciofluvial sandstones, moraines, boulder beds, glacially striated pavements, and other glacially derived geologic structures and beds are also known throughout the southern part of the Arabian Peninsula.[31]

In southern Victoria Land, Antarctica, the Metschel Tillite, made up of reworked Devonian Beacon Supergroup sedimentary strata along with Cambrian and Ordovician granitoids and some Neoproterozoic metamorphic rocks, preserves glacial sediments indicating the presence of major ice sheets. Northern Victoria Land and Tasmania hosted a distinct ice sheet from the one in southern Victoria Land that flowed west-northwestward.[32]

The Sydney Basin of eastern Australia lay at a palaeolatitude of around 60°S to 70°S during the Early and Middle Permian, and its sedimentary successions preserve at least four phases of glaciation throughout this time.[33]

Debate exists as to whether the Northern Hemisphere experienced glaciation like the Southern Hemisphere did, with most palaeoclimate models suggesting that ice sheets did exist in Northern Pangaea but that they were very negligible in volume. Diamictites from the Atkan Formation of Magadan Oblast, Russia have been interpreted as being glacigenic, although recent analyses have challenged this interpretation, suggesting that these diamictites formed during a Capitanian integrlacial interval as a result of volcanogenic debris flows associated with the formation of the Okhotsk–Taigonos Volcanic Arc.[34][35]


Glacial striations formed by late Paleozoic glaciers in the Witmarsum Colony, Paraná Basin, Paraná, Brazil

The evolution of land plants with the onset of the Devonian Period, began a long-term increase in planetary oxygen levels. Large tree ferns, growing to 20 m high, were secondarily dominant to the large arborescent lycopods (30–40 m high) of the Carboniferous coal forests that flourished in equatorial swamps stretching from Appalachia to Poland, and later on the flanks of the Urals. Oxygen levels reached up to 35%,[36] and global carbon dioxide got below the 300 parts per million level,[37] possibly as low as 180 ppm during the Kasimovian,[38] which is today associated with glacial periods. This reduction in the greenhouse effect was coupled with lignin and cellulose (as tree trunks and other vegetation debris) accumulating and being buried in the great Carboniferous Coal Measures. The reduction of carbon dioxide levels in the atmosphere would be enough to begin the process of changing polar climates, leading to cooler summers which could not melt the previous winter's snow accumulations. The growth in snowfields to 6 m deep would create sufficient pressure to convert the lower levels to ice.

Earth's increased planetary albedo produced by the expanding ice sheets would lead to positive feedback loops, spreading the ice sheets still further, until the process hit limit. Falling global temperatures would eventually limit plant growth, and the rising levels of oxygen would increase the frequency of fire-storms because damp plant matter could burn. Both these effects return carbon dioxide to the atmosphere, reversing the "snowball" effect and forcing greenhouse warming, with CO2 levels rising to 300 ppm in the following Permian period. Over a longer period the evolution of termites, whose stomachs provided an anoxic environment for methanogenic lignin-digesting bacteria, prevented further burial of carbon, returning carbon to the air as the greenhouse gas methane.

Once these factors brought a halt and a small reversal in the spread of ice sheets, the lower planetary albedo resulting from the fall in size of the glaciated areas would have been enough for warmer summers and winters and thus limit the depth of snowfields in areas from which the glaciers expanded. Rising sea levels produced by global warming drowned the large areas of flatland where previously anoxic swamps assisted in burial and removal of carbon (as coal). With a smaller area for deposition of carbon, more carbon dioxide was returned to the atmosphere, further warming the planet. Over the course of the Early and Middle Permian, glacial periods became progressively shorter while warm interglacials became longer, gradually transitioning the world from an icehouse to a greenhouse as the Permian progressed.[39] Obliquity nodes that triggered glacial expansion and increased tropical precipitation before 285.1 Mya became linked to intervals of marine anoxia and increased terrestrial aridification after this point, a turning point signifying the icehouse-greenhouse transition.[40] By 250 Mya, planet Earth had returned to a percentage of oxygen similar to that found today.


The development of high-frequency, high-amplitude glacioeustasy, which resulted in sea level changes of up to 120 metres between warmer and colder intervals,[28] during the beginning of the LPIA, combined with the increased geographic separation of marine ecoregions and decrease in ocean circulation it caused in conjunction with closure of the Rheic Ocean, has been hypothesised to have been the cause of the Carboniferous-Earliest Permian Biodiversification Event.[15][41][42]

The rising levels of oxygen during the late Paleozoic icehouse had major effects upon evolution of plants and animals. Higher oxygen concentration (and accompanying higher atmospheric pressure) enabled energetic metabolic processes which encouraged evolution of large land-dwelling arthropods and flight, with the dragonfly-like Meganeura, an aerial predator, with a wingspan of 60 to 75 cm. The herbivorous stocky-bodied and armoured millipede-like Arthropleura was 1.8 metres (5.9 ft) long, and the semiterrestrial Hibbertopterid eurypterids were perhaps as large, and some scorpions reached 50 or 70 centimetres (20 or 28 in).

The rising levels of oxygen also led to the evolution of greater fire resistance in vegetation and ultimately to the evolution of flowering plants.[citation needed]

Milankovitch cycles[edit]

The LPIA, like the present Quaternary glaciation, saw glacial-interglacial cycles governed by Milankovitch cycles acting on timescales of tens of thousands to millions of years. Periods of low obliquity, which decreased annual insolation at the poles, were associated with high moisture flux from low latitudes and glacial expansion at high latitudes, while periods of high obliquity corresponded to warmer, interglacial periods.[43]

Milankovitch cycles profound impacts on marine at the height of the LPIA, with high-latitude species being more strongly affected by glacial-interglacial cycles than low-latitude species.[44]

Also during this time, unique sedimentary sequences called cyclothems were deposited. These were produced by the repeated alterations of marine and nonmarine environments resulting from glacioeustatic rises and falls of sea levels linked to Milankovitch cycles.[45]

See also[edit]


  1. ^ Fedorchuk, Nicholas D.; Griffis, Neil Patrick; Isbell, John L.; Goso, César; Rosa, Eduardo L. M.; Montañez, Isabel Patricia; Yin, Qing-Zhu; Huyskens, Magdalena H.; Sanborn, Matthew E.; Mundil, Roland; Vesely, Fernando F.; Iannuzzi, Roberto (March 2022). "Provenance of late Paleozoic glacial/post-glacial deposits in the eastern Chaco-Paraná Basin, Uruguay and southernmost Paraná Basin, Brazil". Journal of South American Earth Sciences. 106: 102989. doi:10.1016/j.jsames.2020.102989. S2CID 228838061. Retrieved 29 November 2022.
  2. ^ a b c Rosa, Eduardo L. M.; Isbell, John L. (2021). "Late Paleozoic Glaciation". In Alderton, David; Elias, Scott A. (eds.). Encyclopedia of Geology (2nd ed.). Academic Press. pp. 534–545. doi:10.1016/B978-0-08-102908-4.00063-1. ISBN 978-0-08-102909-1. S2CID 226643402.
  3. ^ a b Kent, D.V.; Muttoni, G. (1 September 2020). "Pangea B and the Late Paleozoic Ice Age". Palaeogeography, Palaeoclimatology, Palaeoecology. 553: 109753. doi:10.1016/j.palaeo.2020.109753. S2CID 218953074. Retrieved 17 September 2022.
  4. ^ Montañez, Isabel P.; Poulsen, Christopher J. (2013-05-30). "The Late Paleozoic Ice Age: An Evolving Paradigm". Annual Review of Earth and Planetary Sciences. 41 (1): 629–656. Bibcode:2013AREPS..41..629M. doi:10.1146/ ISSN 0084-6597."The late Paleozoic icehouse was the longest-lived ice age of the Phanerozoic, and its demise constitutes the only recorded turnover to a greenhouse state."
  5. ^ Le Heron, Daniel P.; Kettler, Christoph; Griffis, Neil Patrick; Dietrich, Pierre; Montañez, Isabel Patricia; Osleger, David A.; Hofmann, Axel; Douillet, Guilhem; Mundil, Roland (19 August 2021). "The Late Palaeozoic Ice Age unconformity in southern Namibia viewed as a patchwork mosaic". The Depositional Record. 8 (2): 419–435. doi:10.1002/dep2.163. S2CID 238144156. Retrieved 20 October 2022.
  6. ^ Chen, Bo; Joachimski, Michael M.; Wang, Xiang-dong; Shen, Shu-zhong; Qi, Yu-ping; Qie, Wen-kun (15 April 2016). "Ice volume and paleoclimate history of the Late Paleozoic Ice Age from conodont apatite oxygen isotopes from Naqing (Guizhou, China)". Palaeogeography, Palaeoclimatology, Palaeoecology. 448: 151–161. doi:10.1016/j.palaeo.2016.01.002. Retrieved 5 November 2022.
  7. ^ Fang, Qiang; Wu, Huaichun; Wang, Xunlian; Yang, Tianshui; Li, Haiyan; Zhang, Shihong (1 May 2018). "Astronomical cycles in the Serpukhovian-Moscovian (Carboniferous) marine sequence, South China and their implications for geochronology and icehouse dynamics". Journal of Asian Earth Sciences. 156: 302–315. doi:10.1016/j.jseaes.2018.02.001. Retrieved 5 November 2022.
  8. ^ Huang, He; Gao, Yuan; Jones, Matthew M.; Tao, Huifei; Carroll, Alan R.; Ibarra, Daniel E.; Wu, Huaichun; Wang, Chengshan (15 July 2020). "Astronomical forcing of Middle Permian terrestrial climate recorded in a large paleolake in northwestern China". Palaeogeography, Palaeoclimatology, Palaeoecology. 550: 109735. doi:10.1016/j.palaeo.2020.109735. S2CID 216338756. Retrieved 5 November 2022.
  9. ^ Isbell, John L.; Vesely, Fernando F.; Rosa, Eduardo L. M.; Pauls, Kathryn N.; Fedorchuk, Nicholas D.; Ives, Libby R. W.; McNall, Natalie B.; Litwin, Scott A.; Borucki, Mark K.; Malone, John E.; Kusick, Allison R. (October 2021). "Evaluation of physical and chemical proxies used to interpret past glaciations with a focus on the late Paleozoic Ice Age". Earth-Science Reviews. 221: 103756. doi:10.1016/j.earscirev.2021.103756. Retrieved 27 August 2022.
  10. ^ Fielding, Christopher R.; Frank, Tracy Dagmar; Isbell, John L. (January 2008). "The late Paleozoic ice age--A review of current understanding and synthesis of global climate patterns". Special Paper of the Geological Society of America. 441: 343–354. doi:10.1130/2008.2441(24). ISBN 978-0-8137-2441-6. Retrieved 14 September 2022.
  11. ^ a b c d Yu, H. C.; Qiu, K. F.; Li, M.; Santosh, M.; Zhao, Z. G.; Huang, Y. Q. (5 October 2020). "Record of the Late Paleozoic Ice Age From Tarim, China". Geochemistry, Geophysics, Geosystems. 21 (11): 1–20. doi:10.1029/2020GC009237. S2CID 224922824. Retrieved 29 September 2022.
  12. ^ Pauls, Kathryn N.; Isbell, John L.; McHenry, Lindsay; Limarino, C. Oscar; Moxness, Levi D.; Schencmann, L. Jazmin (November 2019). "A paleoclimatic reconstruction of the Carboniferous-Permian paleovalley fill in the eastern Paganzo Basin: Insights into glacial extent and deglaciation of southwestern Gondwana". Journal of South American Earth Sciences. 95: 102236. doi:10.1016/j.jsames.2019.102236. S2CID 198421412. Retrieved 21 October 2022.
  13. ^ Griffis, Neil Patrick; Montañez, Isabel Patricia; Mundil, Roland; Richey, Jon; Isbell, John L.; Fedorchuk, Nicholas D.; Linol, Bastien; Iannuzzi, Roberto; Vesely, Fernando; Mottin, Thammy; Da Rosa, Eduardo; Keller, Brenhin; Yin, Qing-Zhu (2 October 2019). "Coupled stratigraphic and U-Pb zircon age constraints on the late Paleozoic icehouse-to-greenhouse turnover in south-central Gondwana". Geology. 47 (12): 1146–1150. doi:10.1130/G46740.1. S2CID 210782726. Retrieved 29 November 2022.
  14. ^ Zurli, Luca; Cornamusini, Gianluca; Liberato, Giovanni Pio; Conti, Paolo (15 October 2022). "New data on the Late Paleozoic Ice Age glaciomarine successions from Tasmania (SE Australia)". Palaeogeography, Palaeoclimatology, Palaeoecology. 604: 111210. doi:10.1016/j.palaeo.2022.111210. S2CID 251819987. Retrieved 29 November 2022.
  15. ^ a b c Montañez, Isabel Patricia (2 December 2021). "Current synthesis of the penultimate icehouse and its imprint on the Upper Devonian through Permian stratigraphic record". Geological Society, London, Special Publications. 512: 213–245. doi:10.1144/SP512-2021-124. S2CID 244235424. Retrieved 23 September 2022.
  16. ^ Goddéris, Yves; Donnadieu, Yannick; Carretier, Sébastien; Aretz, Markus; Dera, Guillaume; Macouin, Mélina; Regard, Vincent (10 April 2017). "Onset and ending of the late Palaeozoic ice age triggered by tectonically paced rock weathering". Nature Geoscience. 10 (5): 382–386. doi:10.1038/ngeo2931. Retrieved 14 September 2022.
  17. ^ a b Ezpeleta, Miguel; Rustán, Juan José; Balseiro, Diego; Dávila, Federico Miguel; Dahlquist, Juan Andrés; Vaccari, Norberto Emilio; Sterren, Andrea Fabiana; Prestianni, Cyrille; Cisterna, Gabriela Adriana; Basei, Miguel (22 July 2020). "Glaciomarine sequence stratigraphy in the Mississippian Río Blanco Basin, Argentina, southwestern Gondwana. Basin analysis and palaeoclimatic implications for the Late Paleozoic Ice Age during the Tournaisian". Journal of the Geological Society. 177 (6): 1107–1128. doi:10.1144/jgs2019-214. S2CID 226194983. Retrieved 29 September 2022.
  18. ^ Buggisch, Werner; Joachimski, Michael M.; Sevastopulo, George; Morrow, Jared R. (24 October 2008). "Mississippian δ13Ccarb and conodont apatite δ18O records — Their relation to the Late Palaeozoic Glaciation". Palaeogeography, Palaeoclimatology, Palaeoecology. 268 (3–4): 273–292. doi:10.1016/j.palaeo.2008.03.043. Retrieved 20 October 2022.
  19. ^ Van de Wetering, Nikola; Esterle, Joan S.; Golding, Suzanne D.; Rodrigues, Sandra; Götz, Annette E. (12 November 2019). "Carbon isotopic evidence for rapid methane clathrate release recorded in coals at the terminus of the Late Palaeozoic Ice Age". Scientific Reports. 9 (1): 16544. doi:10.1038/s41598-019-52863-6. PMC 6851110. PMID 31719563.
  20. ^ Chen, Bo; Joachimski, Michael M.; Shen, Shu-zhong; Lambert, Lance L.; Lai, Xu-long; Wang, Xiang-dong; Chen, Jun; Yuan, Dong-xun (July 2013). "Permian ice volume and palaeoclimate history: Oxygen isotope proxies revisited". Gondwana Research. 24 (1): 77–89. doi:10.1016/ Retrieved 10 October 2022.
  21. ^ Cheng, Cheng; Li, Shuangying; Xie, Xiangyang; Cao, Tingli; Manger, Walter L.; Busbey, Arthur B. (15 January 2019). "Permian carbon isotope and clay mineral records from the Xikou section, Zhen'an, Shaanxi Province, central China: Climatological implications for the easternmost Paleo-Tethys". Palaeogeography, Palaeoclimatology, Palaeoecology. 514: 407–422. doi:10.1016/j.palaeo.2018.10.023. S2CID 134157257. Retrieved 29 November 2022.
  22. ^ Chen, Jitao; Montañez, Isabel P.; Zhang, Shuang; Isson, Terry T.; Macarewich, Sophia I.; Planavsky, Noah J.; Zhang, Feifei; Rauzi, Sofia; Daviau, Kierstin; Yao, Le; Qi, Yu-ping; Wang, Yue; Fan, Jun-xuan; Poulsen, Christopher J.; Anbar, Ariel D.; Shen, Shu-zhong; Wang, Xiang-dong (2 May 2022). "Marine anoxia linked to abrupt global warming during Earth's penultimate icehouse". Proceedings of the National Academy of Sciences. 119 (19). doi:10.1073/pnas.2115231119. S2CID 248504537. Retrieved 29 September 2022.
  23. ^ Marchetti, Lorenzo; Forte, Giuseppa; Kustatscher, Evelyn; DiMichele, William A.; Lucas, Spencer G.; Roghi, Guido; Juncal, Manuel A.; Hartkopf-Fröder, Christoph; Krainer, Karl; Morelli, Corrado; Ronchi, Ausonio (March 2022). "The Artinskian Warming Event: an Euramerican change in climate and the terrestrial biota during the early Permian". Earth-Science Reviews. 226: 103922. doi:10.1016/j.earscirev.2022.103922. S2CID 245892961. Retrieved 30 October 2022.
  24. ^ Visser, Johan N. J. (November 1995). "Post-glacial Permian stratigraphy and geography of southern and central Africa: boundary conditions for climatic modelling". Palaeogeography, Palaeoclimatology, Palaeoecology. 118 (3–4): 213–218, 219–220, 223–243. doi:10.1016/0031-0182(95)00008-3. Retrieved 20 October 2022.
  25. ^ Birgenheier, Lauren P.; Frank, Tracy D.; Fielding, Christopher R.; Rygel, Michael C. (15 February 2010). "Coupled carbon isotopic and sedimentological records from the Permian system of eastern Australia reveal the response of atmospheric carbon dioxide to glacial growth and decay during the late Palaeozoic Ice Age". Palaeogeography, Palaeoclimatology, Palaeoecology. 286 (3–4): 178–193. doi:10.1016/j.palaeo.2010.01.008. Retrieved 2 December 2022.
  26. ^ Shi, G. R.; Nutman, Allen P.; Lee, Sangmin; Jones, Brian G.; Bann, Glen R. (February 2022). "Reassessing the chronostratigraphy and tempo of climate change in the Lower-Middle Permian of the southern Sydney Basin, Australia: Integrating evidence from U–Pb zircon geochronology and biostratigraphy". Lithos. 410–411: 106570. doi:10.1016/j.lithos.2021.106570. S2CID 245312062. Retrieved 2 October 2022.
  27. ^ Cheng, Cheng; Wang, Xinyu; Li, Shuangying; Cao, Tingli; Chu, Yike; Wei, Xing; Li, Min; Wang, Dan; Jiang, Xinyi (15 November 2022). "Chemical weathering indices on marine detrital sediments from a low-latitude Capitanian to Wuchiapingian carbonate-dominated succession and their paleoclimate significance". Palaeogeography, Palaeoclimatology, Palaeoecology. 606: 111248. doi:10.1016/j.palaeo.2022.111248. S2CID 252526238. Retrieved 2 December 2022.
  28. ^ a b Rygel, Michael C.; Fielding, Christopher R.; Frank, Tracy D.; Birgenheier, Lauren P. (1 August 2008). "The Magnitude of Late Paleozoic Glacioeustatic Fluctuations: A Synthesis". Journal of Sedimentary Research. 78 (8): 500–511. doi:10.2110/jsr.2008.058. Retrieved 7 October 2022.
  29. ^ Eyles, Nicholas; Young, Grant (1994). Deynoux, M.; Miller, J.M.G.; Domack, E.W.; Eyles, N.; Fairchild, I.J.; Young, G.M. (eds.). Geodynamic controls on glaciation in Earth history, in Earth's Glacial Record. Cambridge: Cambridge University Press. pp. 10–18. ISBN 978-0521548038.
  30. ^ Abbate, Ernesto; Bruni, Piero; Sagri, Mario (2015). "Geology of Ethiopia: A Review and Geomorphological Perspectives". In Billi, Paolo (ed.). Landscapes and Landforms of Ethiopia. World Geomorphological Landscapes. pp. 33–64. doi:10.1007/978-94-017-8026-1_2. ISBN 978-94-017-8026-1.
  31. ^ Senalp, Muhittin; Tetiker, Sema (1 March 2022). "Late Paleozoic (Late Carboniferous-Early Permian) glaciogenic sandstone reservoirs on the Arabian Peninsula". Arabian Journal of Geosciences. 15 (442). doi:10.1007/s12517-022-09467-8. S2CID 247160660. Retrieved 24 August 2022.
  32. ^ Zurli, Luca; Cornamusini, Gianluca; Woo, Jusun; Liberato, Giovanni Pio; Han, Seunghee; Kim, Yoonsup; Talarico, Franco Maria (27 April 2021). "Detrital zircons from Late Paleozoic Ice Age sequences in Victoria Land (Antarctica): New constraints on the glaciation of southern Gondwana". GSA Bulletin. 134 (1–2): 160–178. doi:10.1130/B35905.1. Retrieved 28 September 2022.
  33. ^ Luo, Mao; Shi, G. R.; Lee, Sangmin (1 March 2020). "Stacked Parahaentzschelinia ichnofabrics from the Lower Permian of the southern Sydney Basin, southeastern Australia: Palaeoecologic and palaeoenvironmental significance". Palaeogeography, Palaeoclimatology, Palaeoecology. 541: 109538. doi:10.1016/j.palaeo.2019.109538. S2CID 214119448. Retrieved 5 November 2022.
  34. ^ Davydov, V. I.; Biakov, A. S.; Isbell, John L.; Crowley, J. L.; Schmitz, M. D.; Vedernikov, I. L. (October 2016). "Middle Permian U–Pb zircon ages of the "glacial" deposits of the Atkan Formation, Ayan-Yuryakh anticlinorium, Magadan province, NE Russia: Their significance for global climatic interpretations". Gondwana Research. 38: 74–85. doi:10.1016/ Retrieved 29 September 2022.
  35. ^ Isbell, John L.; Biakov, Alexander S.; Vedernikov, Igor L.; Davydov, Vladimir I.; Gulbranson, Erik L.; Fedorchuk, Nicholas D. (March 2016). "Permian diamictites in northeastern Asia: Their significance concerning the bipolarity of the late Paleozoic ice age". Earth-Science Reviews. 154: 279–300. doi:10.1016/j.earscirev.2016.01.007. Retrieved 27 August 2022.
  36. ^ Robert A. Berner (1999). "Atmospheric oxygen over Phanerozoic time". PNAS. 96 (20): 10955–7. Bibcode:1999PNAS...9610955B. doi:10.1073/pnas.96.20.10955. PMC 34224. PMID 10500106.
  37. ^ Peter J. Franks, Dana L. Royer, David J. Beerling, Peter K. Van de Water, David J. Cantrill, Margaret M. Barbour and Joseph A. Berry (16 July 2014). "New constraints on atmospheric CO2 concentration for the Phanerozoic". Geophysical Research Letters. 31 (13): 4685–4694. Bibcode:2014GeoRL..41.4685F. doi:10.1002/2014GL060457. hdl:10211.3/200431. S2CID 55701037.{{cite journal}}: CS1 maint: multiple names: authors list (link)
  38. ^ Richey, Jon D.; Montañez, Isabel P.; Goddéris, Yves; Looy, Cindy V.; Griffis, Neil P.; DiMichele, William A. (22 September 2020). "Influence of temporally varying weatherability on CO2-climate coupling and ecosystem change in the late Paleozoic". Climate of the Past. 16 (5): 1759–1775. doi:10.5194/cp-16-1759-2020. S2CID 225046506. Retrieved 5 October 2022.
  39. ^ Garbelli, C.; Shen, S. Z.; Immenhauser, A.; Brand, U.; Buhl, D.; Wang, W. Q.; Zhang, H.; Shi, G. R. (15 June 2019). "Timing of Early and Middle Permian deglaciation of the southern hemisphere: Brachiopod-based 87Sr/86Sr calibration". Earth and Planetary Science Letters. 516: 122–135. doi:10.1016/j.epsl.2019.03.039. S2CID 146718511. Retrieved 27 August 2022.
  40. ^ Fang, Qiang; Wu, Huaichu; Shen, Shu-zhong; Fan, Junxuan; Hinnov, Linda A.; Yuan, Dongxun; Zhang, Shihong; Yang, Tianshui; Chen, Jun; Wu, Qiong (June 2022). "Astronomically paced climate evolution during the Late Paleozoic icehouse-to-greenhouse transition". Global and Planetary Change. 213: 103822. doi:10.1016/j.gloplacha.2022.103822. S2CID 248353840. Retrieved 17 October 2022.
  41. ^ Shi, Yukun; Wang, Xiangdong; Fan, Junxuan; Huang, Hao; Xu, Huiqing; Zhao, Yingying; Shen, Shuzhong (September 2021). "Carboniferous-earliest Permian marine biodiversification event (CPBE) during the Late Paleozoic Ice Age". Earth-Science Reviews. 220: 103699. doi:10.1016/j.earscirev.2021.103699. Retrieved 4 September 2022.
  42. ^ Groves, John R.; Yue, Wang (1 September 2009). "Foraminiferal diversification during the late Paleozoic ice age". Paleobiology. 35 (3): 367–392. doi:10.1666/0094-8373-35.3.367. S2CID 130097035. Retrieved 4 September 2022.
  43. ^ Fang, Qiang; Wu, Huaichun; Hinnov, Linda A.; Tian, Wenqian; Yang, Xunlian; Yang, Tianshui; Li, Haiyan; Zhang, Shihong (April 2018). "Abiotic and biotic responses to Milankovitch-forced megamonsoon and glacial cycles recorded in South China at the end of the Late Paleozoic Ice Age". Global and Planetary Change. 163: 97–108. doi:10.1016/j.gloplacha.2018.01.022. Retrieved 24 November 2022.
  44. ^ Badyrka, Kira; Clapham, Matthew E.; López, Shirley (1 October 2013). "Paleoecology of brachiopod communities during the late Paleozoic ice age in Bolivia (Copacabana Formation, Pennsylvanian–Early Permian)". Palaeogeography, Palaeoclimatology, Palaeoecology. 387: 56–65. doi:10.1016/j.palaeo.2013.07.016. S2CID 42512923. Retrieved 24 November 2022.
  45. ^ Van den Belt, Frank J. G.; Van Hoof, Thomas B.; Pagnier, Henk J. M. (1 August 2015). "Revealing the hidden Milankovitch record from Pennsylvanian cyclothem successions and implications regarding late Paleozoic chronology and terrestrial-carbon (coal) storage". Geosphere. 11 (4): 1062–1076. doi:10.2110/jsr.2008.058. Retrieved 5 November 2022.